THE SEDIMENTARY CHARACTERISTICS OF DAGPAZARI PATCH REEF (MIDDLE MIOCENE, MUT - ICELITURKEY) 'Murat Giil and 2Muhsin Eren 'Department of Geology, Cukurova University, 01330, Balcali, Adana, TURKEY; [email protected] 2Department of Geology, Mersin University, Ciftlikkoy Kampusu, Icel, TURKEY; [email protected] ABSTRACT: Thisstudyaimsto determine faciescharacteristics of theDagpazaripatchreef(MiddleMiocene)locatedat 13km northofthe Mut (Icel) town.Mut (Icel) andnearbyareasaregeologically known asMut Basinsituatedin the CentralTaurides. Inthe MutBasin,MiddleMiocene timeisrepresentedby Mut and Koselerliformations. The Mut Formationcomprisesreeflimestoneand interfingers withthe Koselerli Formation consistingof claystone,argillaceouslimestone andmarl. Dagpazaripatch reef has a gentle and elongateddome shape. Its elongation extends in NW -SE direction. In the Dagpazaripatch reef and its surroundings, fivelithofaciesandseveralsubfacieshavebeen delineatedbasedmainlyon reefgeometryandalsomacroandmicrofaciesfeatures. Thispatchreefisapproximately 15 mthick,500 m in lengthand 200 minwidth. Theseare; I) Basefacies(redalgalwackestone-packstone, Dunham 1962; biomicrite, Folk 1962); 2) Reefcorefacies(coral-redalgalframestone-bindstone, EmbryandKlovan 1971; biolithite, Folk 1962); gastropodpelecypodwackestone-packstone, biomicrite; grainstone,biosparite); 3) Fore reef-flankfacies(planktonic foraminiferal-red algalwackestone, biomicrite); 4) Back reef-flank facies (wackestone, biomicrite; local framestone-bindstone, biolithite); 5) Sealing facies (echinoid-intraclast packstone-grainstone, biointramicrite, biointrasparite). Reef core faciesis easily separatedfromotherreeffacies by: i) presenceof frame-building organisms(coral);ii) presenceof bindingorganisms (redalgae,bryozoa);and iii)diversefauna. Reef-flankfaciesare separatedfromreefcorefaciesdueto theirwell-beddedappearance. Thesealing facies truncatesthe other reef units with an erosionalsurface. Faciesandframe-building organismswerehighlyaffectedby sea-level fluctuation duringtheLanghian. Grainstone (Dunham 1962) occurredwhere the environment iscloseto wavebase;planktonic foraminiferal wackestone (Dunham 1962) depositedwheretheenvironmentwasrelatively deep. In overall,the Dagpazaripatch reef was depositedin shallowenvironment. Keywords: Patchreef,MiddleMiocene,Mut (Icel/Turkey), sedimentology, environment.

INTRODUCTION Mut (Icel) and nearby areas are geologically known as a Mut basin located in the central segment of the Taurus Mountains. Taurus Mountains, which are situated along the southern boundary of Turkey, are traditionally divided into western, central and eastern segments, based mainly on geography (Fig. 1). Basement rocks crop out in the southern part of the Mut basin. Oligocene - Basal Miocene sedimentary units unconformably overlie emplaced Neotethyan units. Burdigalian alluvial and deltaic deposits are passing into the lacustrine to shallow marine clastic-carbonate sediments. Thick reef limestones, including very well exposed patch reefs developed during Langhian-Early Serravalian time (Gedik et a1. 1979). Mut and Koselerli formations represent Middle Miocene time in Mut basin. The Mut Formation comprises reef limestone which grades into the Koselerli Formation consisting claystone, argillaceous limestone and marl. Both formations interfinger with each other. In the Mut Formation, patch reefs are abundant and form present day topographical rises at the Ardicli hill, Zincirkaya hill, Ikiz hill, etc., similar to pre-existing topographical rises in the depositional environment. The Mut Basin has been received a wide attention of investigators (Gokten 1976; Gedik et al. 1979; Tanar 1989; Carbonates and Evaporites, v. 18 , no. 1, 2003, p. 51-62.

Giirbiiz and Ucar 1999). However, studies upon patch reefs are very limited such as Atabey (1999) who has studied some mound and lens shaping carbonate build-ups in the Mut Formation. This study aims to determine sedimentary characteristics of the Dagpazari patch reef, which is situated at 13km north ofthe Mut (Icel) town. The road goes from Mut to Dagpazari plateau crosscuts the Dagpazari patch reef and presents a spectacular view for research.

METHODS Ten stratigraphic sections were measured to characterize the Dagpazari patch reef More than one hundred samples were collected. Thin sections were prepared from the samples and examined under a petrographic microscope. Each sample has been classified using classifications of Folk (1962) and Dunham (1962) with modifications of Embry and Klovan (1971).

STRATIGRAPHIC SETTING The rock association in the Mut Basin is divided into two groups Miocene and Pre-Miocene rocks (Ozdogan and Sahbaz 1999). The basement of the Mut basin consists of Palaeozoic

THE SEDIMENTARY CHARACTERISTICS OF DAGPAZARI PATCH REEF

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THE SEDIMENTARY CHARACTERISTICS OF DAGPAZARI PATCH REEF Miocene sedimentary units unconformably overlie the Cretaceous limestone and ophilotic melange (Gedik et al. 1979). The oldest Cenozoic unit in the basin is Lower Oligocene conglomerate, sandstone, shale, marl and siltstone.

argillaceous limestone and marl (Figs. 2-3). DAGPAZARI PATCH REEF Geometry

Tertiary units unconformably overlie the Upper Cretaceous Limestone in the study area. The oldest Tertiary unit is represented by Derincay Formation (Early Miocene), which consists mainly of red-green colored conglomerate and sandstone of alluvial deposits and deltaic deposits (Figs. 2- 3).

Dagpazari patch reef has a gentle and elongated dome shape. The reef is approximately 15 meters thick, 500 m in length and 200 m in width. Its elongation extends SW-NE direction. Base facies is situated at the bottom level of the other reef facies, and it has a transitional contact with Koselerli Formation and unconformably overlies the Upper Cretaceous limestone. Back reef-flank beds have dipping towards to north. Fore reefflank beds have dippingtowards to open sea in the southernpart of the reef and grade into Koselerli Formation argillaceous limestone-marl. Sealing carbonate truncates the reef core and reef-flank beds with an erosional surface (Fig. 4).

Middle Miocene in the basin is characterized by Mut, Koselerli and Dagpazari formations. Mut Formation consists of reef limestones deposited in shallow marine environment and distinctive patch reefs are common in this formation such as Dagpazari patch reef Koselerli Formation comprises claystone, argillaceous limestone and marl deposited in the centre of the basin (Gedik et al. 1979; Atabey et al. 2000). Dagpazari Formation (Serravalian) contains lagoonal and alluvial deposits, and crops out at the northern part of the Mut basin (Atabey et al. 2000). These three Middle Miocene formations interfinger with each other (Figs. 2- 3).

Reef Facies In the Dagpazari patch reef and its surroundings, five lithofacies and several subfacies have been delineated based on mainly reef geometry and also macro and micro facies properties (Figs. 4 -5). These lithofacies are: (a) Base facies (red algal wackestone-packstone, Dunham 1962; biomicrite, Folk 1962); (b) Reef core facies (coral-red algal framestonebindstone, Embry and Klovan 1971; biolithite; gastropod-

Late Miocene aged Tirtar and Balli formations unconformably overlie Middle Miocene sedimentary units. Both formations also interfinger with each other. Tirtar Formation consists of reef limestone. Balli Formation contains claystone-

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GUL, EREN, AND DERMAN pelecypod wackestone-packstone; biomicrite; grainstone, biosparite); (c) Fore reef-flank facies (planktonic foraminiferal and red algal wackestone, biomicrite); (d) Back reefflank facies (wackestone, biomicrite; local bindstoneframestone, biolithite); and (e) Sealing facies (echinoid and intraclast packstone-grainstone, biomicrite-biointrasparite). The distributions of the facies are shown in the figure 5. Reef core facies constitute the main part ofthe Dagpazari patch reef body.

a) Base Facies.- This facies, which is gradational with the Koselerli Formation, is placed at the bottom of the Dagpazari patch reef facies. It is gray-ash coloured and massive limestone. This facies consists of bioclastic wackestonebiomicrite. Base facies is mainly covered by slope debris due to road construction, for this reason extension of it is not entirely followed in the study area. The major component of this facies is red alga, abundant pelecypod, echinoid and rarely planktonic foraminifera, Globigerinatheka sp. (in the southern part of reef area; (Fig. 5). Base facies deposited in shallow marine (relatively deeper, probably less than 50 m) environment during the Langhian transgression over the topographical rises which consist of Upper Cretaceous limestone. b) ReefCore Facies.- Reef core facies is main part of the reef having a gentle and elongated dome-shape, it is surrounded by the flank beds (Figs. 4-5). The reef core facies is represented by light grey, yellow-cream colored, massive limestone. This massive limestone illustrates horizontal and wavy fractures (Fig 4). Vertical and micritic sedimentary dykes are also present in reef core. This facies is 500 m in length, 200 m in width and 15-20 m in height (Figs. 4-5). It can be clearly distinguished from other reef facies by: (i) the presence of frame-building organisms such as coral; Dendrophyllia cf. candelabrum HENNIG, Litharaeopsis subepithe cata (OPPENHEIM), Porites sp., Favites sp.; (ii) the presence of binding organisms such as red algae; Mesophyllum cf. guamense JOHNSON, Amphiroa propria (LEMOINE), Corallina cf. abundans LEMOINE, Lithothamnium sp., Lithophyllum sp., Archaeolithathamnium sp., Jania sp., Halimeda sp., and bryozoa; (iii) diverse fauna including benthic foraminifers; Peneroplis evolutus HENSON, Peneroplis cf. thomasi HENSON, Peneroplis cf. forsensis HENSON, Gyroida cf. subangulata (PLUMMER), Borelis cf. melo curdica (REICHEL), Idalina aff. sinjarica GRIMSDALE, Archaias kirkukensis HENSON, Praerhapydionina cf. huberi HENSON, Delheidia hayderiei DOUVILLE, Peneroplis sp., Gyroidina sp., Operculina sp., Anomalina sp., Opthalmidium sp., Quinqueloculina sp., Textularia sp., Rotalia sp., Planorbulina sp., Neoalveolina sp., Pentelline sp., Triloculina sp., Nodosaria sp., and pelecypod, echinoid, gastropod, ostracod, (Calvet and Tucker 1995). Fossil community of Dagpazari patch reef was determined by Prof. Dr. Nurdan lNAN (Mersin University). These fossil groups especially Borelis cf. melo curdica (REICHEL), Peneroplis evolutus HENSON, Peneroplis cf. 57

thomasi HENSON, Peneroplis cf. forsensis HENSON, Archaias kirkukensis HENSON and Delheidia hayderiei DOUVILLE indicate the Langhian-Serravalian (Middle Miocene) age. Microscopic studies reveal that the reef core facies is made up by following subfacies; (l) Coral-red algal framestonebindstone (Embry and Klovan 1971), biolithite (Folk 1962) subfacies; (2) Gastropod-pelecypod wackestone-packstone (Dunham 1962), biomicrite (Folk 1962) subfacies; (3) Grainstone (Dunham 1962), biosparite (Folk 1962) subfacies. 1) Coral-Red algal framestone-bindstone, biolithite subfacies: This subfacies consists of yellow-cream, massive, abundant wavy fractured and nodular reef limestone (Fig. 4). Main components of this subfacies are coral, red algae, bryozoa, benthic foraminifera, pelecypod, echinoid, and ostracod. Coral colonies have a branching morphology (Fig. 6A-B) and their height is change between 0.3 to 0.7 m. In general, the colonies are in growth position (Fig. 4). Solitary corals are also observed in this subfacies. Red algae play major role in reef core facies development. Encrusting red algae and bryozoa covers coral and stabilizes this rigid reef frame (Fig. 6C). The interstices between the coral colonies are filled by red algal, coral, bryozoa fragments, pelecypod, gastropod benthic foraminifera and micrite (Fig. 6D-E). At the beginning fibrous marine calcite cement filled space among the grains, but later under meteoric diagenesis, equitant calcite blocky cement filled space among the grains (Fig. 6F). This subfacies creates main rigid structure of the Dagpazari patch reef. It produces a wave resistant mound shape and also source of the flank facies component. 2) Gastropod-pelecypod bearing wackestone-packstone, biomicrite subfacies: This subfacies is pale yellow, massive, wavy fractured and cracked (Fig. 6D) wackestone-packstone, biomicrite. Primary components of this subfacies are gastropod, pelecypod, coral, red algae, echinoid fragments and benthic foraminifera (Fig. 6E). It is observed among the coral colonies. 3) Grainstone subfacies: Megascopically, it is pale yellow, white and cream, massive, abundant wavy fractured and cracked. The components ofthis subfacies are similar to other reef core subfacies. It is formed where the sea wave active. Two generation of calcite cement are present, the first consist of fibrous calcite cement. Second generation of cement consist ofequitant blocky sparite that fills the space among the grains (Fig. 6F). Reef core organisms indicated that this facies was deposited in clear, warm shallow marine environment. The subfacies distribution and organic composition (Figs. 5-6) were highly affected by sea-level fluctuation. Where the environment get close to wave base and in the high nutrient level area, coral

THE SEDIMENTARY CHARACTERISTICS OF DAGPAZARI PATCH REEF

Figure 6. Photographs of Dagpazari patch reef facies: A) Coral framestone-biolithite in reef core facies, the spaces between the coral filled by equitant calcite cement, Coral: Dendrophyllia cf candelabrum HENNIG, (thin section: D7.12). B) Coral bindstone-biolithite in reef core facies, Coral: Litharaeopsis subepithe cata OPPENHEIM, (thin section: D6.5). C) Red algae bindstone-biolithite in reefcore facies, Red algae: Mesophyllum cf guamense JOHNSON, (thin section: D7.9). D) Macroscopic view of the Gastropod-bivalve packstone-biomicrite subfacies in reef core, G: Gastropoda. E) Wackestone-packstone-biomicrite subfacies which is fill the spaces among the framestone and bindstone, A: Archaias kirkukensis HENSON, 0: Operculina sp. (thin section: D4.10). F) Marine cement in reefcore, fibrous marine cement at the margin, equitant calcite cement at the centre. G) Fore reef-flank deposits wackestone-biomicrite, G: Giobigerinetheka sp., R: reworked red algae fragment, E: Echinoid, (thin section: DlO.5). H) Sealing facies, intraclast packstone-grainstone, intramicrite-intrasparite, I: intraclast. 58

GOL, EREN, AND DERMAN colonies grew up in different places of the Dagpazari patch reef over the base facies. Then encrusting red algae and bryozoa stabilize the reef frame. Initially fibrous calcite cement filled space in and around the coral colonies. When the environment was far away from the wave base and relatively deepening, wackestone and packstone that contains the coral and red algae fragments, in situ benthic foraminifera, pelecypod, gastropod, deposited among the coral colonies. Also abundance of geopetal structures in reef core is other evidence for sea-level fluctuation. c) Fore ReefFlank Facies>- It consists of yellow and cream, thin to medium layered (5 em to 30-50 em), planktonic foraminiferal and red algal wackestone, biomicrite. This facies is separated in two parts as an inner and outer. Inner fore reef-flank layers are placed on the side of the reef and apparently steeply inclines at an angle of approximately 45 0. Inner fore reef-flank, which comprise thinly well-bedded limestones, is 30-35 m in length and 4 m thick. Reworked fossils and debris falls are common in this facies. Coral colonies lost their initial position due to transportation in this debris block. Outer reef-flank layers that are gradational with Koselerli Formation marl and argillaceous limestone at the far away from the reef consist of nearly horizontally layered wackestone, biomicrite. Outer reef-flank is over 500 m in length and over 10 m thick (Fig. 4). The main components of this facies are red algae, bryozoa, echinoid, pelecypod fragment, planktonic foraminifera (Globigerinatheka sp.), rarely, benthic foraminifera (Delheidia hayderiei DOUVILLE, Borelis cf. melo curdica (REICHEL), Operculina sp. Textularia sp., Anomalina sp., Peneroplis sp.), and intraclast. Also some big reef core blocks are observed in this facies. The percentage of coral debris and reworked reef fossils within the fore reef-flank beds decreases away from the reef (Fig. 6G). Fore reef-flank facies deposited in relatively deeper region on the southern slope of reef mound and developed towards the open sea. It is observed in D 8, 9, 10 stratigraphic sections (Fig. 5). When amount of transporting material was increasing, packstone deposited in the fore reef-flank area. Planktic organisms are the main components of this facies. d) Back Reef Facies.- It is situated northern part of the Dagpazari patch reef. This facies consist of yellow-cream, medium to thickly bedded (25-60 em) reeflirnestone. It is 63 m in length and 13 m thick. Back reef facies layers have dipping towards to north approximately 30°-45° (Figs. 4-5). As a result of petrographic analysis, two subfacies have been distinguished; 1) Wackestone, biomicrite subfacies; 2) Local bindstone-framestone, biolithite subfacies.

were broken and transported from reef core, and benthic foraminifera. Rarely planktonic foraminifera is observed where the environment was relatively deep. 2) Local bindstone-framestone, biolithite subfacies: It occurred among the wackestone subfacies where the environmental condition is suitable. This subfacies consists of primarily red algae, coral and benthic foraminifera (especially Operculina sp.), pelecypod, and echinoid. Back reef-flank beds are deposited in relatively deeper region at the northern slope of the reef core mound. Depends on an amount of transporting materials come from reef core, generally wackestone deposited. However when the environment get closes to wave base, become a clear and warm, some local framestone-bindstone occurrences are also observed in this facies. e) Sealing Facies> This facies truncates and discordantly overlies the all reef units with an erosive surface (Fig. 4). It comprise of massive, grey-dark grey, echinoid and intraclast packstone-grainstone, biomicrite-biosparite. Sealing facies thickness is exceeding the 70-80 meters. The length of this facies is over the 900-1000 m. Main components of this facies are echinoid fragment, intraclast, red algae and pelecypod fragments (Fig. 6H). Grainstone development and intraclast existence indicated that sealing facies was deposited in high energy, shallow marine environment.

DAGPAZARIREEFEVOLUTION The complex relict topography of the Mut basin was flooded during the Miocene by a rapid marine transgression, when it was connected with open sea (the Neotethys) through a small seaway in the Silifke area (Buchem et al. 2001). Topographically higher transgressive surface offer a suitable place for reef development, and recent reef hill, which has an erosional contact with the older units, in Mut and its surroundings indicate paleotopographical rises in the Mut basin. Claystone and marl alternation (Koselerli Formation) was deposited among the Mut Formation reefs and relatively deep basin region (Gurbuz and Ucar 1999; Fig. 7). The major controlling factor on the sedimentation pattern are fluctuations in relative sea-level, but depositional geometries, texture and lithology are demonstrated to be extremely variable and controlled by paleotopography and ecological change (Buchem et al. 2001). The main and subfacies distribution and Dagpazari patch reef biotic composition clearly show that this situation. Dagpazari patch reef has a gradational contact with Koselerli Formation and unconformably overlies the Upper Cretaceous limestone. When the environment becomes clear, get shallow and warm during the Langhian transgression, base facies (wackestone-packstone; biomicrite) are deposited. Mainly red algae, pelecypod, echinoid and rarely planktonic foraminifera are observed in this facies. Then the reef core

1) Wackestone, biomicrite subfacies: This subfacies is pale yellow-cream, thin to medium layered, wackestone, biomicrite. Major components of it are red algae, coral, bryozoa, echinoid, pelecypod fragments, intraklast, which

59

THE SEDIMENTARY CHARACTERISTICS OF DAGPAZARI PATCH REEF Dagpazan Formation

Figure 7. Illustrative model showing a paleoenvironmental interpretation of the Mut basin during the Mut Formation reef limestone deposition (modified from Giirbiiz and Ucar 1999).

facies developed over the base facies and it contains three subfacies. These are framestone-bindstone (biolithite), gastropod-red algal wackestone-packstone (biomicrite) and grainstone (biosparite). This subfacies variation, biotic composition of it and abundance of geopetal structures indicate the sea-level fluctuation during the Dagpazari patch reef development. Coral colonies generally prefer the clear, well oxygenated, warm and high nutrient environment (Hayward et al. 1992; Calvet and Tucker 1995). Also Dagpazari patch reef coral colonies grew up in similar environment. Encrusting red algae and bryozoa stabilized this rigid coral frame (Strasser and Strohmenger 1997). This rigid organic mound produces a barrier against the sea wave. So it creates a suitable environment for carbonate precipitation. Gastropod and pelecypod wackestone and packstone fill the space among the framestones and bindstones. This subfacies also contains coral, red algal and bryozoa fragments, which don't show reworking mark, and benthic foraminifera. In Dagpazari patch reef core, these bioclastic wackestone and packstone reflect sedimentation in quiet water (Strasser and Strohmenger 1997). When the environment goes far from the wave base, wackestone and packstone deposited depends on an amount of grains. When the environment gets close to wave base, it becomes a suitable for coral and red algae development, so framestone and bindstone deposited. The presence of grainstone especially in southern part of the Dagpazari patch reef is a probably reflection ofthe pumping of the seawater through the porous reefal facies, because bioclastic grainstone are deposited in reef body exposed the wave action (Calvet and Tucker 1995). Two generation of calcite cement were observed in Dagpazari patch reef. Initially fibrous marine calcite cement precipitated among the grains. Then equitant blocky calcite cement filled the spaces among the grains under the effects ofmeteoric diagenesis. The faunal change in the reef may be related to change in nutrient supply (Calvet and Tucker 1995). High biotic diversity in reef core indicates the high nutrient level area. Towards to flank

decreasing biotic diversity indicates the lower nutrient level. Broken pieces of reef core were transported backward and in front of the reef area. This pieces and local organisms constitute well-bedded flank deposits. Fore reef-flank deposits are separated in two parts. These are inner and outer parts fore reef-flank. Inner layers are placed on the side of the reef and apparently steeply incline at an angle of approximately 45°. Outer layers are placed far away from the reef and it is gradational with Koselerli Formation claystone and argillaceous limestone. The percentage of coral debris and reworked fossils within the fore reef-flank beds decrease away from the reef. Back reef-flank reef layers are situated northern part of the reef and have dipping approximately 30°45°. Some local bindstone occurrences are observed where the environment condition was suitable in back reef-flank deposits. All reef occurrences are truncated by sealing facies that contains intraclast and echinoid bearing packstone-grainstone with erosive surfaces. Also geopetal structures in the reef core indicate the atmospheric effect over the Dagpazari patch reef.

CONCLUSIONS Five distinct lithofacies and several subfacies are delineated depending on reef geometry, macro and microfacies features. These are; a) Base facies; b) Reef core facies; c) Fore reefflank facies; d) Back reef-flank facies; and e) Sealing facies. Base facies consists of red algal, abundant pelecypod wackestone-biomicrite, deposited in shallow marine water, and gradationally overlie the Koselerli Formation. Reef core facies contains coral-red algal framestone-bindstone (biolithite), pelecypod-gastropod wackestone-packstone (biomicrite) and grainstone (biosparite). This facies is easily

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GUL, EREN, AND DERMAN separated from other reef facies by: i) presence of coral; ii) presence of red algae and bryozoa; iii) diverse fauna. Fore reef-flank and back reef-flank facies are easily recognized due to their well-bedding appearances. Inner fore reef-flank layers are placed on the side of the reef and apparently steeply inclined at an angle of approximately 45°. Nearly horizontally layered outer fore reef-flank is gradationally passed into the Koselerli Formation claystone and argillaceous limestone. Sealing facies truncates all other reef facies with an erosive surface. This erosive surface and geopetal structures clearly show atmospheric effects over the Dagpazari patch reef It contains intraclast and echinoid packstone-grainstone (biomicrite-biosparite), which were deposited in relatively higher energy environment. Facies and biotic composition in Dagpazari patch reef were highly affected by sea-level fluctuation, nutrient level, hydrodynamic stress, base topography and wave action.

ACKNOWLEDGMENTS This paper forms a part of the MSc thesis of the first author (Giil2001) which was supervised by second co-author (Dr. M. Eren). Mersin University Research Fund financially supported this research. We would like to express our sincere thanks to Dr. A. Sami Derman for introducing the Dagpazari patch reef Appreciation is extended to Prof Dr. Nurdan Inan (Mersin University) for the identification of the fossil assemblage, and also to A. Ozbek (Cukurova University) and Mersin University Mut Vocational High School staff for their assistance in the fieldwork.

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